Medlicott: Sub-Himalayan Series in Jamu. 
55 
PART 2.] 
would seem to be one of comparative depression ; although, of coui’se, the deepest section visible, 
the lower zones of rock are not so exposed along it as on parallel sections to the south-east. 
The river itself observes no rule in its windings amongst the points of these opposing 
flexures. 
I could detect nothing definite in these mutually accommodating structural features to 
prove that either system is younger or older than the other. They fit into each other in a way 
that could only be effected by a simultaneous growth. The continuity of strike observable in 
each could not obtain if the strata had previously been affected by undulations of the other. 
Of the two, however, the strikes are much more steady in the north-west south-east system; 
a fact which may, perhaps, suggest that they had somewhat the start in their alignment. The 
great Bakrala flexure is almost serpentine in its windings. The form also of the north-east 
south-west flexures is less regular ; and in its variation betrays the dominance of the Hima¬ 
layan thrust: while to the south-west, the steep side of these flexures is almost uniformly on 
the south-east; to the north-east the steeper side is to the north-west. It is so in the Lehri 
anticlinal, and in the Bakrala flexure north of the Kasi. 
In following the tertiary zones south-westwards from the Himalayan border to the Salt 
Range, some important changes are very marked. As is usual in the proximity of all the great 
Himalayan rivers, the Siwalik conglomerates attain an enormous special development near 
the Jhelam. They are finely exposed in the hills west of Salgraon, where it is well seen how 
this character is due partly to encroachment upon the lower zone. When not in force, the 
conglomerates are confined to the topmost earthy-brown portion of the series; this band 
is largely represented here ; but below it the grey sandstone is strongly conglomeratic for a 
thickness of several hundred feet. These coarse deposits decrease greatly to the south, and 
become confined to the topmost beds, as described by Mr. Wynne in the Kharian or Pabbi 
hills, south-east of Jhelam (Bee. Geol. Surv., Ind., Vol. VIII, p. 48). 
The main fossiliferous zone of the Siwaliks continues in great force to the south. The 
uncertainty of our measurements of them does not admit as yet of any close comparison in 
this respect. Mr. Theobald has again during this season made a good collection from these 
beds, principally in the area immediately north of the Salt Range, between the Tilla and 
Bakrala ridges. Mr. Lydekher, when he returns from the field, will no doubt give a good 
account of them. 
In the lower zone we again find a very marked contrast from north to south along the 
Jhelam, between the Sub-Himalayan region and the Salt Range. We have seen all along 
the former ground that the Subathu-Dagshai boundary is the most unsettled of any in the 
Sub-Himalayan tertiary series; stray thin layers of nnmmulitic limestone being locally 
found high up in the purple clays transitionally overlying the distinctive Subathu zone. In 
the Salt Range, on the contrary, this is the most marked boundary of any; thick, softish 
sandstones and clays rest abruptly on the clear nummulitic limestone. The commonest junc¬ 
tion-layer being a conglomerate made up of water-worn pebbles of the limestone and its 
flints, I described the contact in my Memoir of 1862 (p. 91), as one of denudation. I do not 
think the term a misleading one for such a junction, although Mr. Wynne very properly 
insists upon the constant parallelism of the stratification in the two groups, and upon his 
failure to find even a single case of actual erosion in the lower group filled in by the upper one. 
It is quite evident, however, that a very considerable break in the tertiary series occurs at 
this horizon in the Salt Range, amounting, I should think, to several hundred feet of the 
Subathu and immediately supra-Subathu zones of the Himalayan sections. 
An important formation not yet mentioned came largely under our notice in the Sub- 
Himalayan hills—high-level river-shingle capping the ridges and spurs of upturned tertiary 
strata and packed against their flank at fully 400 to 500 feet over the actual river courses, 
which must have been eroded to at least that depth since the period of these deposits. There 
is evidence also to show that to some extent at least this was a re-excavation of the channels out 
